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Basin-Related Effects on Ground Motion for Earthquake Scenarios In Geophys. J. Int. (2006) 166, 197–212 doi: 10.1111/j.1365-246X.2006.02909.x Basin-related effects on ground motion for earthquake scenarios in the Lower Rhine Embayment ∗ Michael Ewald,1 Heiner Igel,1 Klaus-G¨unterHinzen2 and Frank Scherbaum3 1Department of Earth and Environmental Studies, Section Geophysics, Ludwig-Maximilians-University M¨unchen, Germany 2Abt. f¨urErdbebengeologie, University Cologne, Germany 3Institut f¨urGeowissenschaften, University of Potsdam, Germany Accepted 2006 January 11. Received 2006 January 8; in original form 2005 March 20 Downloaded from https://academic.oup.com/gji/article/166/1/197/632062 by guest on 24 September 2021 SUMMARY The deterministic calculation of earthquake scenarios using complete waveform modelling plays an increasingly important role in estimating shaking hazard in seismically active regions. Here we apply 3-D numerical modelling of seismic wave propagation to M 6+ earthquake scenarios in the area of the Lower Rhine Embayment, one of the seismically most active regions in central Europe. Using a 3-D basin model derived from geology, borehole information and seismic experiments, we aim at demonstrating the strong dependence of ground shaking on hypocentre location and basin structure. The simulations are carried out up to frequencies of ca. 1 Hz. As expected, the basin structure leads to strong lateral variations in peak ground motion, amplification and shaking duration. Depending on source–basin–receiver geometry, the effects correlate with basin depth and the slope of the basin flanks; yet, the basin also affects peak ground motion and estimated shaking hazard thereof outside the basin. Comparison with measured seismograms for one of the earthquakes shows that some of the main characteristics of the wave motion are reproduced. Cumulating the derived seismic intensities from the three modelled earthquake scenarios leads to a predominantly basin correlated intensity distribution for our study area. Key words: deterministic shaking hazard, earthquake scenarios, numerical wave propagation, seismic intensities, site effects. GJI Seismology also been studied for various earthquakes in the vicinity of the Los INTRODUCTION Angeles Basin (e.g. Vidale & Helmberger 1988; Scrivner & The study area, the Lower Rhine Embayment (LRE) is part of the Helmberger 1994; Olsen et al. 1997; Olsen 2000). European rift system (Fig. 1) and shows moderate intraplate seis- The LRE was subject to intensive studies on ground motion am- micity. On average, several earthquakes of magnitude 5 and higher plification, especially after the damaging 1992 Roermond, M 5.9 occur every century (Reamer & Hinzen 2004). The LRE cuts as earthquake. Most of these investigations focused on 1-D estimation a sedimentary basin into the Rhenish Massif with a general NW– of site amplification based on spectral ratios of local seismicity and SE strike of the major faults. In its western part, the Roer Val- ambient noise measurements (e.g. Ibs-von Seht & Wohlenberg 1999; ley Graben (RVG) sediment layers exceed 1.5 km thickness. The Scherbaum et al. 2003; Ohrnberger et al. 2004; Hinzen et al. 2004; whole basin is densely populated and highly industrialized with Parolai et al. 2005). While these techniques give valid estimates on large petrochemical and chemical plants. Basins of such structure are 1-D amplification factors, they do not provide information on 3-D known to significantly amplify ground motions during earthquakes. effects, such as wave front focusing due to low-velocity zones or Striking examples are the damages in the Mexico City, M 8.1, edge-diffracted waves. 3-D wave propagation simulations account Michoacan earthquake (Sing & Ordaz 1993; C´ardenas& Ch´avez- for such issues and can, therefore, provide additional information on Garcia 2003) and in parts of San Francisco during the 1989 Loma basin-related seismic hazard. The 1995 Hyogo-Ken Nanbu, M 6.9 Prieta, M 7 earthquake (Stidham et al. 1999). The variability of earthquake near the city of Kobe, Japan, drastically proved the im- ground motion due to lateral variations in sediment thickness has portance of 3-D effects on the wavefield (e.g. Kawase 1996; Pitarka & Irikura 1996a). Numerous other studies concentrated on this is- sue (e.g. Boore 1972; Olsen et al. 1995a,b; Pitarka & Irikura 1996b; Graves 1998; Satoh et al. 2001). ∗ Corresponding author: Department f¨urGeo- und Umweltwissenschaften, Several recent studies on southern California and the Los Sektion Geophysik, Theresienstr. 41 80333 M¨unchen,Germany. E-mail: Angeles basin showed significant lateral variations of ground mo- [email protected] tion due to 3-D geologic structures (e.g. Olsen et al. 1997; Olsen C 2006 The Authors 197 Journal compilation C 2006 RAS 198 M. Ewald et al. 2000; Peyrat et al. 2001; Eisner & Clayton 2002; Komatitsch et al. as the LRE and a moderate seismicity leading to earthquakes with 2004). Incorporating complex kinematic finite sources, advantage predominantly dip-slip mechanisms. Arrows in Fig. 1 indicate the is taken of the detailed knowledge of the corresponding earthquake main directions of extensional stress in this region. Stress inversion source processes due to dense strong motion observations as well as from fault plane solutions of 110 earthquakes in the northern Rhine the high-resolution 3-D model of the Los Angeles Basin (Magistrale area (Hinzen 2003) indicates a subvertical direction of the largest et al. 1998, 2000; S¨uss& Shaw 2003). principal stress in the LRE. However, in the neighboring Stavelot- In this pilot study of earthquake ground motion in parts of the Venn Massif and Rhenish Massif the maximum principal stress is LRE the basin structure is represented by a 3-D model with depth subhorizontal. The maximum horizontal compressional stress in the dependent velocity and uniform attenuation upon layered bedrock. area has a trend of 125◦. The scenario earthquakes are modelled as finite-source moment tensors. We present three simulations of damaging earthquakes that oc- Seismicity curred in the LRE within the last 250 yr using a 3-D staggered-grid Together with the Belgian zone, the RVG belongs to the seismically finite-difference technique (e.g. Igel et al. 1995; Graves 1996). The most active onshore zones in northwestern Europe. Its active tec- Downloaded from https://academic.oup.com/gji/article/166/1/197/632062 by guest on 24 September 2021 spatial and temporal discretization allows us to simulate the wave- tonic extension regime makes it to one of the few areas in Europe field for frequencies up to 1 Hz. The main goal of this study is to north of the Alps producing damaging earthquakes. From histori- investigate the complexity of the resulting wavefield and the effects cal records more than 20 damaging earthquakes in the past 300 yr of amplification and prolonged shaking due to 3-D effects of the are known (Schwarzbach 1951). Local magnitudes of the strongest sedimentary basin in the study area. The key questions we want to historic earthquakes, 1976 D¨urenand 1692 Verviers were estimated address are: (1) How does the basin model alter the peak values of to 6.4 and 6.8 (Hinzen & Oemisch 2001), respectively. Probabilis- ground motion? (2) Where—with respect to the basin geometry— tic seismic hazard analysis of this region estimates an intensity VII are amplifications to be expected? (3) How does the basin affect occurrence rate of 10−3 yr−1 (Rosenhauer & Ahorner 1994). The hazard estimates derived from peak ground motion? main present day seismic activity is observed in the RVG and its sur- The results from this study reveal strong lateral heterogeneity roundings. Within the last century 38 earthquakes with magnitudes in the distribution of peak ground velocities (PGV) and shaking M L ≥ 4.0 occurred in the northern Rhine area (Reamer & Hinzen duration due to the basin topography and the source location. Seis- 2004). Since 1755, the RVG and its extensions have experienced mogram sections illustrate the different effects of amplified and at least nine earthquakes with M L ≥ 5.0. The earthquakes of 1756 prolonged shaking and demonstrate the intrinsic 3-D nature of the D¨uren, M L 6.1, 1951 Euskirchen, M L 5.7 and the 1992 Roermond phenomena. Regions dominated by intraplate tectonics are charac- event M L 5.9 have been chosen as scenarios in this study. The M L terized by low deformation rates and long recurrence times for large 4.9 Alsdorf, 2002 July 22, event is by now the only larger local earthquakes. Consequently, the strong motion database is sparse for earthquake recorded by the seismic network in the LRE. Analysis such areas and shaking hazard assessment is afflicted with large un- of this earthquake and modelling of the observations allowed the certainties. Our results, therefore, further emphasize the need for appraisal of the current basin model (Ewald 2005). It was shown detailed 3-D basin models and accurate ground motion modelling that—despite of local discrepancies—peak ground motions for fre- in order to assess seismic hazard in the LRE and similar regions of quencies up to 1 Hz were reproduced for stations located throughout interest. the basin with a maximum deviation factor of two. STUDY AREA—THE LOWER RHINE Basin model EMBAYMENT The sediments in the Lower Rhine Embayment have accumulated Location since the Carboniferous age. This long period results in a complex stratigraphy with locally varying thickness of the different sequences The LRE is a sedimentary basin located in the northwestern part of (Geluk et al. 1994). In this study the stratigraphy is represented by Germany, parts of the Netherlands and Belgium. Its shape is roughly a 3-D structure of soft sediments embedded by a layered bedrock a northwest opening triangle. The northern extension is called West model. Seismic velocities within the sediments increase smoothly Netherlands Basin ending at the North Sea coast. The close-up map with depth.
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